Serpukhovian

The Serpukhovian Stage was proposed in 1890 by Russian stratigrapher Sergei Nikitin and was introduced in the official stratigraphy of European Russia in 1974. It was named after the city of Serpukhov, near Moscow. The ICS later used the upper Russian subdivisions of the Carboniferous in its international geologic time scale. The base of the Serpukhovian is informally defined by the first appearance of the conodont Lochriea ziegleri, though the utility and systematic stability of this species is not yet certain. No lower GSSP has been assigned to the Serpukhovian Stage yet. Two candidate GSSPs have been proposed: the Verkhnyaya Kardailovka section in the South Urals of Russia, and the Naqing (Nashui) section in Guizhou, China. It is also slightly above the first appearance of the foram Globivalvulina bulloides, genozone of the ammonoid genus Homoceras and the ammonoid biozone of Isohomoceras subglobosum. == Subdivision == Biostratigraphy In Europe, the Serpukhovian Stage includes three conodont biozones: the Gnathodus postbilineatus Zone (youngest), Gnathodus bollandensis Zone, and Lochriea ziegleri Zone (in part, oldest). There are three foraminifera biozones: the Monotaxinoides transitorius Zone (youngest), Eostaffellina protvae Zone, and Neoarchaediscus postrugosus Zone (oldest). In North America, the stage encompassed four conodont biozones: the Rhachistognathus muricatus Zone (youngest), Adetognathus unicornis Zone, Cavusgnathus naviculus Zone, and Gnathodus bilineatus Zone (in part, oldest). Regional subdivisions In the regional stratigraphy of Russia (and Eastern Europe as a whole), the Serpukhovian is subdivided into four substages, from oldest to youngest: the Tarusian, Steshevian, Protvian, and Zapaltyubian. The former three are found in the Moscow Basin and are named after places near Serpukhov (Tarusa and Protva). Strata belonging to the Zapaltyubian are not exposed in the Moscow Basin, though they are found in the Donets Basin and the Urals. In North America, the Serpukhovian corresponds to the upper part of the Chesterian regional stage, while in China the Serpukhovian is roughly equivalent to the Dewuan regional stage. == Serpukhovian extinction ==

The largest extinction event of the Carboniferous Period occurred in the early Serpukhovian. This extinction came in the form of ecological turnovers, with the demise of diverse Mississippian assemblages of crinoids and rugose corals. After the extinction, they were replaced by species-poor cosmopolitan ecosystems. The extinction selectively targeted species with a narrow range of temperature preferences, as cooling seawater led to habitat loss for tropical specialists. Ammonoids appear to have not been impacted by this event, as they reached a zenith in diversity at this time. The long-term ecological impact of the Serpukhovian extinction may have exceeded that of the Ordovician-Silurian extinction, where taxonomic diversity was abruptly devastated but quickly recovered to pre-extinction levels. Sepkoski (1996) plotted an extinction rate of around 23-24% for the Serpukhovian as a whole, based on marine genera which persist through multiple stages. Bambach (2006) found an early Serpukhovian extinction rate of 31% among all marine genera. Using an extinction probability procedure generated from the Paleobiology Database, McGhee et al. (2013) estimated an extinction rate as high as 39% for marine genera. Relative to other biological crises, the Serpukhovian extinction was much more selective in its effects on different evolutionary faunas. Stanley (2007) estimated that the early Serpukhovian saw the loss of 37.5% of marine genera in the Paleozoic evolutionary fauna. Only 15.4% of marine genera in the modern evolutionary fauna would have been lost along the same time interval. This disconnect, and the severity of the extinction as a whole, is reminiscent of the Late Devonian extinction events. Another similarity is how the Serpukhovian extinction was seemingly driven by low rates of speciation, rather than particularly high rates of extinction. with this stagnation in biological diversity driven by a reduction of carbonate platforms, which otherwise would have helped to maintain high biodiversity. More recent studies have instead argued that biodiversity surged during the LPIA in what is known as the Carboniferous-Earliest Permian Biodiversification Event (CPBE). Foraminifera especially saw extremely rapid diversification. The CPBE may have been caused by the dramatically increased marine provincialism resulting from sea level fall during the LPIA, combined with the assembly of Pangaea, which limited the spread of taxa from one region of the world ocean to another. == See also ==